Common Reflection Azimuth Migration

ABSTRACT

Method for migration of seismic data into datasets having common azimuth angle at the reflection point. A velocity model is selected that prescribes subsurface P and/or S wave velocities including any required anisotropy parameters. ( 41 ) For shot locations on a surface grid, rays are traced on to a 3D grid of points in a target region of the subsurface. ( 42 ) At least the travel times of the rays and their dip angles at each subsurface point are stored in computer memory as they are computed. ( 43 ) Using the stored ray maps, the seismic data are migrated into seismic image volumes, each volume being characterized by at least an azimuthal angle bin, the azimuthal angles being computed from said ray dip angle information. ( 44 )

CROSS-REFERENCE TO RELATED APPLICATIONS

This application claims the benefit of U.S. Provisional application61/095,013 which was filed on Sep. 8, 2008.

FIELD OF THE INVENTION

This invention relates generally to the field of geophysicalprospecting, and more particularly to seismic data processing.Specifically, the invention is a method for migration of seismic datainto datasets having common azimuth angle at the reflection point.

BACKGROUND OF THE INVENTION

The present invention may be regarded as an extension of U.S. Pat. No.7,095,678 “Method for seismic imaging in geologically complexformations” to Winbow and Clee, which document is incorporated byreference into the disclosure herein.

The technical problem primarily addressed herein is the class of depthimaging situations where azimuth information at each image point isneeded. Such azimuth information should take account of 3D variation ofvelocity and anisotropy as well as the dip of the target reflectors.Such information is useful in understanding the fracture properties ofcarbonate reservoirs found, for example, in the Caspian and the MiddleEast. Such fracture information is important to efficient hydrocarbonexploration of and production from such reservoirs because it is animportant influence on the porosity and permeability of petroleumreservoirs. Present ray based imaging methods such as Kirchhoff arecomputationally efficient but are limited to producing seismic volumesthat have constant surface (i.e. source-receiver) azimuth. This isbecause the maps used in the migration only contain travel times andtherefore are unable to direct the output into files depending onreflection angle or reflection point azimuth. Wave equation basedmethods are more time consuming and expensive than ray based imagingmethods. Therefore there is a need for a ray-based method that canobtain azimuthal information at the reflection points. The method shouldmigrate 3D seismic data into common reflection point azimuth seismicvolumes using ray based imaging methods, where the azimuths are definedat the image point and are valid for any dip of the target reflector.The method should be applicable for any acquisition geometry whether itis land data, bottom cable data or marine data, provided that thesubsurface is not so complex that it requires wave equation methods toform adequate images.

SUMMARY OF THE INVENTION

In one embodiment, the invention is a method for migrating 3D seismicdata to create depth images of reflector surfaces in a subsurface regionwhere azimuth information at each image point is desired for petroleumexploration or production, said method comprising performing steps(a)-(c) one data trace at a time:

(a) for each combination of the trace's corresponding seismic source andreceiver locations and an image point, using a ray-based imaging methodto determine direction angles at the image point of a first seismic rayconnecting the source to the image point and of a second seismic rayconnecting the receiver location to the image point;

(b) geometrically determining mathematical relationships from whichazimuthal angle at the image point of a plane defined by each first andsecond seismic ray pair can be solved knowing the ray direction angles;and

(c) migrating the seismic data trace into data volumes labeled by acommon azimuthal angle of the rays at each image point.

BRIEF DESCRIPTION OF THE DRAWINGS

The present invention and its advantages will be better understood byreferring to the following detailed description and the attacheddrawings in which:

FIG. 1 is a diagram showing the geometry for P-P common reflection anglemigration;

FIG. 2 is a diagram defining angles used in the present inventivemethod;

FIG. 3 is a diagram showing the geometry for P-S imaging; and

FIG. 4 is a flow chart showing steps in one embodiment of the presentinventive method.

The invention will be described in connection with example embodiments.However, to the extent that the following description is specific to aparticular embodiment or a particular use of the invention, this isintended to be illustrative only, and is not to be construed as limitingthe scope of the invention. On the contrary, it is intended to cover allalternatives, modifications and equivalents that may be included withinthe scope of the invention, as defined by the appended claims.

DETAILED DESCRIPTION OF EXAMPLE EMBODIMENTS

The Common Reflection Angle Migration (“CRAM”) approach to imagingdisclosed in U.S. Pat. No. 7,095,678 is particularly well suited to theclass of imaging problems described above (in the “Background” section).This is because a key feature of CRAM is that, given a velocity model(step 41 in the flow chart of FIG. 4) and a sufficiently detailed raytracer such as the commercially available software code NORSAR-3D, thetravel time, amplitude, surface dip and image point dip are known forall rays in the one-way ray maps. This applies whether the imaging isP-P, P-S, or S-S, and whatever anisotropy is or is not included. For thepresent purpose, a key point is that the dip directions of the one-wayrays at each reflector point are stored in the mapping phase and areavailable to the migration kernel. The CRAM patent (U.S. Pat. No.7,095,678) is incorporated by reference herein in its entirety.

FIG. 1 illustrates the geometry for P-P CRAM. (PP means that theincident seismic wave is a P-wave, and it reflects as a P-wave.) Ray 1connects the seismic source 11 to the image (i.e., reflection) point 13,while Ray 2 connects the receiver location 12 to the image point. Inpreferred embodiments of the invention, these rays are traced by raytracer software for seismic shot locations on a surface grid on to a 3Dgrid of points in a target region of the subsurface (Step 42 in FIG. 4).What follows, through equation 16 is a description of how the azimuthalangles are computed from ray dip angles, i.e. from angles made byone-way rays at the reflection point with respect to the normal to thereflector surface at that point (see step 44 of FIG. 4). Note that theterms “image point” and “reflection point” are used somewhatinterchangeably herein, with the understanding that there is adifference in precise meaning: an image point may or may not turn out tobe a reflection point, according to whether the migration process findsor does not find a reflector at an image point.

As described by U.S. Pat. No. 7,095,678, ray direction unit vectors{circumflex over (n)}₁₀, {circumflex over (n)}₂₀ give the directions ofeach ray at the surface while ray direction unit vectors {circumflexover (n)}₁, {circumflex over (n)}₂ give the ray directions at the imagepoint. Herein, all symbols that have a caret (̂) appearing over themrefer to unit vectors. The unit dip vector {circumflex over (n)} bisectsthe angle between {circumflex over (n)}₁ and {circumflex over (n)}₂, andits components may be referred to as the dip, or dip direction,corresponding to the ray pair and image point 13. The colatitude angle θand longitude angle φ specify the Cartesian components of {circumflexover (n)} in the standard way:

{circumflex over (n)}_(x)=sin θ cos φ

{circumflex over (n)}_(y)=sin θ sin φ

{circumflex over (n)}_(z)=cos θ  (1)

The angle α is the reflection angle and the angle ψ is the azimuthangle. As stated in U.S. Pat. No. 7,095,678: “The angle ψ around therotation axis defined by {circumflex over (n)} determines theorientation of the plane defined by the rays at the image point. Informing the seismic image the angle ψ is usually summed over, which canbe accomplished by ignoring it in the kernel. However, if ψ is computedin the kernel, it is also possible to produce seismic volumes thatdepend on both ψ and the reflection angle α.” The present invention is amethod for doing this.

The angle α can be computed from the equation:

cos(2α)={circumflex over (n)} ₁ ·{circumflex over (n)} ₂   (2)

Vectors {circumflex over (n)} and {circumflex over (m)} can be foundfrom:

{circumflex over (n)}=({circumflex over (n)} ₁ +{circumflex over (n)}₂)/(2 cos α)   (3)

{circumflex over (m)}=({circumflex over (n)} ₂ −{circumflex over (n)}₁)/(2 sin α)   (4)

Vectors {circumflex over (n)} and {circumflex over (m)} are thereforemutually perpendicular and are coplanar with {circumflex over (n)}₁ and{circumflex over (n)}₂. The vector {circumflex over (m)} is related toangle ψ as explained below. FIG. 2 contains the information needed toexpress the azimuth angles in terms of the vectors {circumflex over (m)}and {circumflex over (n)}. The orientation of the reflection planedefined by {circumflex over (m)} and {circumflex over (n)} orequivalently {circumflex over (n)}₁ and {circumflex over (n)}₂ isdefined by the composite of three rotations:

R(ψ,θ,φ)=R _(z)(ψ)R _(y)(θ)R _(z)(φ)   (5)

The initial configuration has vectors {circumflex over (n)}₁ and{circumflex over (n)}₂ in the x-z plane each making an angle α with thez-axis along which {circumflex over (n)} is pointed. The succession ofrotations of the coordinate axes in equation (5) corresponds to the“y-convention” described at greater length by Goldstein (ClassicalMechanics, Addison-Wesley, 147 (1981)). That is, the rotations are, inorder, around the z-axis by an angle φ, followed by rotation around thenew y-axis by an angle θ, followed by rotation around the new z-axis byan angle ψ. The vector {circumflex over (n)} points along the finalz-axis while the vectors {circumflex over (l)} an {circumflex over (k)}point along the x and y-axes after the second rotation R_(y)(0). Thevectors {circumflex over (z)}, {circumflex over (n)} and {circumflexover (l)} lie in a plane that intersects the x-y plane in a line definedby the unit vector {circumflex over (λ)}. The vectors {circumflex over(n)} and {circumflex over (m)} define a plane that meets the x-y planein a line defined by the vector {circumflex over (μ)}. The vector{circumflex over (μ)} defines the azimuthal direction of the reflectingrays relative to a fixed direction in space, taken here as the x-axis.The angle ε is defined by:

cos ε={circumflex over (x)}·{circumflex over (μ)}  (6)

This angle coincides with the angle φ defined by Biondi (Biondo Biondi,3D Seismic Imaging, Society of Exploration Geophysicists, Ch. 6 (2006)).The angle ψ is the azimuthal angle relative to the dip direction of theimaged reflector.

The unit vectors {circumflex over (l)} and {circumflex over (k)}arerelated to angles θ and φ:

{circumflex over (l)}=(cos θ cos φ,cos θ sin φ,−sin θ)   (7)

and,

{circumflex over (k)}=(−sin φ,cos φ,0)   (8)

One way to compute the angle ψ is from the simultaneous equations:

$\begin{matrix}{\begin{pmatrix}{\cos \; \psi} \\{\sin \; \psi} \\0\end{pmatrix} = {\begin{bmatrix}\hat{l} \\\hat{k} \\\hat{n}\end{bmatrix}\hat{m}}} & (9)\end{matrix}$

The azimuthal angle ε can be computed from the ray directions as:

$\begin{matrix}{{\tan \; ɛ} = \frac{{n_{2\; y}/n_{2\; z}} - {n_{1\; y}/n_{1\; z}}}{{n_{2\; x}/n_{2\; z}} - {n_{1\; x}/n_{1\; z}}}} & (10)\end{matrix}$

Equation (10) is equivalent to a formula of Biondi and Palacharla(Geophysics 61, 1822-1832 (1996)) and Biondi (3D Seismic Imaging, Ch 6,Society of Exploration Geophysicists (2006)). However, these referencespresent it in a wave equation imaging context instead of the ray basedimaging context of the present invention. The methods described in the2006 Biondi reference are focused on downward continuation imagingmethods, which are much more time consuming and expensive than the raybased imaging methods used in the present invention. Chapter 6 givesvarious formulas and comments based on wave equation imaging withoutdisclosing how to process seismic data to produce common azimuthal anglesections. Other examples of a common azimuth downward continuationmethod include U.S. Pat. No. 6,778,909 to Popovici et al.; and Prucha etal., SEP (Stanford Exploration Project) Report 100, pp 101-113 (1999).Only reflection angles are considered. Azimuth angles are treated onlywith the assumption that azimuth is constant in depth, which is notgenerally true in depth imaging.

The angle ψ can be most efficiently computed as:

$\begin{matrix}{{\tan \; \psi} = \frac{\tan \left( {ɛ - \varphi} \right)}{\cos \; \theta}} & (11)\end{matrix}$

where θ and φ can be calculated from equations (1).

For interpretation of the fracture angles in seismic data both angles εand ψ may be required, depending on the complexity of the fracturesystem under investigation. This is because the angle ε refers to theazimuthal angle relative to a fixed direction in space, in this caserelative to the x-axis. The angle ψ refers to the azimuth relative tothe direction of dip of the reflector. Both fracture patterns are foundin fractured rocks in real world geology.

These formulas apply to the case of P-P reflection imaging. For the caseof P-S imaging which is also important for investigating fractures(since S-waves are more sensitive to fractures than P-waves), all of theabove formulas apply except for the definitions of vectors {circumflexover (m)} and {circumflex over (n)} which have to be redefined in termsof {circumflex over (n)}₁ and {circumflex over (n)}₂ as shown in FIG. 3.In this case the incidence angle of the P-wave relative the reflectornormal {circumflex over (n)} is α, and the angle of the departing S-waverelative to the reflector normal is β. For P-S imaging the vectors{circumflex over (m)} and {circumflex over (n)} can be computed asfollows.

First the total reflection angle α+β is calculated by:

cos(α+β)={circumflex over (n)} ₁ ·{circumflex over (n)} ₂   (12)

Then the individual angles α and β are computed from:

$\begin{matrix}{{\sin \; \alpha} = \frac{\sin \left( {\alpha + \beta} \right)}{\left\lbrack {\left\{ {{v_{S}/v_{P}} + {\cos \left( {\alpha + \beta} \right)}} \right\}^{2} + {\sin^{2}\left( {\alpha + \beta} \right)}} \right\rbrack^{1/2}}} & (13) \\{{\sin \; \beta} = {\left( {v_{S}/v_{P}} \right)\sin \; \alpha}} & (14)\end{matrix}$

where v_(S) and v_(P) are respectively the S- and P-wave velocities atthe image point.With this information the reflector normal can be constructed as:

$\begin{matrix}{\hat{n} = \frac{{{\hat{n}}_{1}\sin \; \beta} + {{\hat{n}}_{2}\sin \; \alpha}}{\sin \left( {\alpha + \beta} \right)}} & (15)\end{matrix}$

The unit vector {circumflex over (m)} that describes (through itsrotation around the normal {circumflex over (n)}) the azimuth angle ψ atthe reflection point is in the plane of the reflector and is:

$\begin{matrix}{\hat{m} = \frac{{{\hat{n}}_{1}\cos \; \beta} + {{\hat{n}}_{2}\cos \; \alpha}}{\sin \left( {\alpha + \beta} \right)}} & (16)\end{matrix}$

The angle ε can be computed from equation 10. The angle ψ can becomputed from equations 1 and 11. Alternatively, equations 1, 10, and 11can be used.

As explained in the previous section, the best way to implementmigration into common azimuth datasets is to first compute one-way raymaps that contain at a minimum (see step 43 in FIG. 4):

(1) travel times

(2) dip values at the target locations

Normally, (as explained in U.S. Pat. No. 7,095,678) the ray maps used inCRAM would also contain amplitudes, KMAH indices and dip vectors at thesource locations. As explained in the previous section the angles α, ψ,and ε can be computed from {circumflex over (n)}₁ and {circumflex over(n)}₂. This applies for both P-P and P-S imaging. The unusual case ofS-P imaging is the same as P-S imaging with source and receiverexchanged, while the case of S-S imaging is similar to the case of P-Pimaging with S-wave velocities substituted for P-wave velocities. Thusfar herein, only isotropic media have been explicitly considered;however anisotropic media can be dealt with in the same way.

Koren et al. describe a local angle domain (“LAD”) for use in seismicimaging. (Paper 297, EAGE 69^(th) Conference & Exhibition, London, Jun.11-14, 2007) Their LAD is a system of four angles defining theinteraction between incident and reflected waves at a specific imagepoint. Two angles represent the spatial direction of the ray-pathnormal: its dip and azimuth. The third angle is the half-opening anglebetween the incident and reflected rays. The fourth angle is the azimuthof the ray-pair plane measured in the ray-pair reflection surface. InU.S. Patent Application Publication No. 2008/0109168 (May 8, 2008),Koren and Ravve use the LAD angles in angle-domain imaging of seismicdata. They map the seismic data set to a second data set of lowerdimensionality, and then image the second set of data. This approach iscomputer intensive, and may be impractical for 3D seismic data sets. Incontrast, the present inventive method reads in a data trace, computesthe reflection and azimuth angles on the fly using stored dipinformation as explained in detail in the CRAM patent (U.S. Pat. No.7,095,678), and migrates that trace before the next data trace is readinto the computer. This results in an advantageous savings of computertime and resources.

The method for performing migration in the present invention ispreferably but not necessarily CRAM. For example, the seismic data maybe migrated into common offset data volumes, common shot volumes, orcommon receiver volumes. (Step 44 in FIG. 4) The scope of the presentinvention includes all such migration methods.

It will be understood by those skilled in the art that the methodsdescribed herein enable migration into volumes that are labeled byazimuth and/or reflection angle in any way convenient for the end user.This is because determining the angles 60 , ψ and/or ε on the fly in themigration kernel makes it possible to “scatter” the migration outputinto volumes appropriately labeled by α, ψ and/or ε.

The foregoing application is directed to particular embodiments of thepresent invention for the purpose of illustrating it. It will beapparent, however, to one skilled in the art, that many modificationsand variations to the embodiments described herein are possible. Allsuch modifications and variations are intended to be within the scope ofthe present invention, as defined in the appended claims.

1. A method for migrating 3D seismic data to create depth images ofreflector surfaces in a subsurface region where azimuth information ateach image point is desired for petroleum exploration or production,said method comprising performing steps (a)-(c) one data trace at atime: (a) for each combination of the trace's corresponding seismicsource and receiver locations and an image point, using a ray-basedimaging method to determine direction angles at the image point of afirst seismic ray connecting the source to the image point and of asecond seismic ray connecting the receiver location to the image point;(b) geometrically determining mathematical relationships from whichazimuthal angle at the image point of a plane defined by each first andsecond seismic ray pair can be solved knowing the ray direction angles;and (c) migrating the seismic data trace into data volumes labeled by acommon azimuthal angle of the rays at each image point.
 2. The method ofclaim 1, wherein the mathematical relationships also allow solving forreflection angle, being the angle between said first and second rays,and wherein the seismic data trace is migrated into data volumes labeledby common reflection angle as well as azimuthal angle of the rays ateach image point.
 3. The method of claim 2, wherein the method iscomputer implemented and the migrating uses stored dip information todetermine the reflection angle and azimuthal angle from the mathematicalrelationships, for each trace separately during imaging.
 4. The methodof claim 1, further comprising: (d) using the azimuthal angles atreflection points to interpret the subsurface region's petroleumpotential.
 5. The method of claim 4, wherein the azimuthal angles areused to understand fracture or anisotropy properties of the subsurfaceformation.
 6. The method of claim 1, wherein the mathematicalrelationships provide a solution for the azimuthal angle either relativeto a global system of coordinates or relative to the ray pair's dipdirection at the image point.
 7. The method of claim 1, furthercomprising computing ray maps containing at least travel times and dipvalues at image points.
 8. The method of claim 7, wherein the method iscomputer implemented and the direction angles of the first and secondrays at each image point are stored in the ray maps, available to amigration kernel performing step (c).
 9. The method of claim 1, whereinthe azimuthal angle ε relative to the x-axis of a fixed (x,y,z)coordinate system is calculated from an equation that may be expressedas${\tan \; ɛ} = \frac{{n_{2\; y}/n_{2\; z}} - {n_{1\; y}/n_{1\; z}}}{{n_{2\; x}/n_{2\; z}} - {n_{1\; x}/n_{1\; z}}}$where the terms on the right hand side are Cartesian components of unitvectors {circumflex over (n)}₁, {circumflex over (n)}₂ whichrespectively give directions of the first and second seismic rays. 10.The method of claim 9, wherein the azimuthal angle ψ relative to the raypair's dip direction at the image point is calculated from an equationthat may be expressed as${\tan \; \psi} = \frac{\tan \left( {ɛ - \varphi} \right)}{\cos \; \theta}$wherein θ and φ are calculated from{circumflex over (n)}_(x)=sin θ cos φ{circumflex over (n)}_(y)=sin θ sin φ{circumflex over (n)}_(z)=cos θ where {circumflex over (n)} is unit dipvector for the ray pair at the image point.
 11. The method of claim 10,wherein the seismic data being imaged is P-P or S-S data, and{circumflex over (n)} is calculated from{circumflex over (n)}=({circumflex over (n)} ₁ +{circumflex over (n)}₂)/(2 cos α) where α is the reflection angle calculated fromcos(2α)={circumflex over (n)}₁ ·{circumflex over (n)} ₂
 12. The methodof claim 10, wherein the seismic data being imaged is P-S or S-P data,and {circumflex over (n)} is calculated from$\hat{n} = \frac{{{\hat{n}}_{1}\sin \; \beta} + {{\hat{n}}_{2}\sin \; \alpha}}{\sin \left( {\alpha + \beta} \right)}${circumflex over (n)}={circumflex over (n)} ₁ sin β+{circumflex over(n)} ₂ sin α/sin(α+β) where α+β is calculated fromcos(α+β)={circumflex over (n)} ₁ ·{circumflex over (n)} ₂ and individualangles αand β are computed from:${\sin \; \alpha} = \frac{\sin \left( {\alpha + \beta} \right)}{\left\lbrack {\left\{ {{v_{S}/v_{P}} + {\cos \left( {\alpha + \beta} \right)}} \right\}^{2} + {\sin^{2}\left( {\alpha + \beta} \right)}} \right\rbrack^{1/2}}$sin  β = (v_(S)/v_(P))sin  α where v_(S) and v_(P) are respectivelyS-wave and P-wave velocity in the subsurface region at the image point.13. The method of claim 1, wherein the seismic data being imaged is P-Por S-S data and wherein the azimuthal angle ψ relative to the ray pair'sdip direction at the image point is calculated by solving simultaneousequations that may be expressed as $\begin{pmatrix}{\cos \; \psi} \\{\sin \; \psi} \\0\end{pmatrix} = {\begin{bmatrix}\hat{l} \\\hat{k} \\\hat{n}\end{bmatrix}\hat{m}}$ where{circumflex over (n)}=({circumflex over (n)} ₁ +{circumflex over (n)}₂)/(2 cos α){circumflex over (m)}=({circumflex over (n)} ₂ −{circumflex over (n)}₁)/(2 sin α) and reflection angle α is computed fromcos(2α)={circumflex over (n)} ₁ ·{circumflex over (n)} ₂ where unitvectors {circumflex over (n)}₁, {circumflex over (n)}₂ respectively givedirections of the first and second seismic rays, and unit vectors{circumflex over (l)} and {circumflex over (k)} are related to angles θand φ:{circumflex over (l)}=(cos θ cos φ,cos θ sin φ,−sin θ)and,{circumflex over (k)}=(−sin φ,cos φ,0) where 0 and φ are related to afixed (x,y,z) coordinate system by{circumflex over (n)}_(x)=sin θ cos φ{circumflex over (n)}_(y)=sin θ sin φ.{circumflex over (n)}_(z)=cos θ
 14. The method of claim 1, wherein theseismic data being imaged is P-S or S-P data and wherein the azimuthalangle ψ relative to the ray pair's dip direction at the image point iscalculated by solving simultaneous equations that may be expressed as$\begin{pmatrix}{\cos \; \psi} \\{\sin \; \psi} \\0\end{pmatrix} = {\begin{bmatrix}\hat{l} \\\hat{k} \\\hat{n}\end{bmatrix}\hat{m}}$ where {circumflex over (n)} is unit dip vectorfor the ray pair at the image point and is calculated from$\hat{n} = \frac{{{\hat{n}}_{1}\sin \; \beta} + {{\hat{n}}_{2}\sin \; \alpha}}{\sin \left( {\alpha + \beta} \right)}$where α+β is calculated fromcos(α+β)={circumflex over (n)} ₁ ·{circumflex over (n)} ₂ and individualangles α and β are computed from:${\sin \; \alpha} = \frac{\sin \left( {\alpha + \beta} \right)}{\left\lbrack {\left\{ {{v_{S}/v_{P}} + {\cos \left( {\alpha + \beta} \right)}} \right\}^{2} + {\sin^{2}\left( {\alpha + \beta} \right)}} \right\rbrack}$sin  β = (v_(S)/v_(P))sin  α where v_(s) and v_(p) are respectivelyshear wave and P-wave velocity in the subsurface region at thereflection point, and unit vector {circumflex over (m)} is perpendicularto {circumflex over (n)} and is given by$\hat{m} = \frac{{{\hat{n}}_{1}\cos \; \beta} + {{\hat{n}}_{2}\cos \; \alpha}}{\sin \left( {\alpha + \beta} \right)}$and unit vectors {circumflex over (l)} and {circumflex over (k)} arerelated to angles θ and φ:{circumflex over (l)}=(cos θ cos φ,cos θ sin φ,−sin θ)and,{circumflex over (k)}=(−sin φ,cos φ,0) where θ and φ are related to afixed, global (x,y,z) coordinate system by{circumflex over (n)}_(x)=sin θ cos φ{circumflex over (n)}_(y)=sin θ sin φ.{circumflex over (n)}_(z)=cos θ
 15. The method of claim 1, furthercomprising geometrically determining mathematical relationships fromwhich reflection angle of each ray can be solved knowing the raydirection angles; and migrating the seismic data into data volumeslabeled by reflection angle as well as azimuthal angle.
 16. The methodof claim 15, wherein the seismic data are migrated using CommonReflection Angle Migration (“CRAM”).
 17. The method of claim 16, whereinmigrating the seismic data into data volumes specified by azimuthalangle and reflection angle comprises the computer implemented steps: (i)discretizing all or part of the subsurface region containing a targetformation into a three-dimensional grid of image cells, each such imagecell containing a plurality of points of a pre-selectedthree-dimensional image point grid, cell dimensions being chosen tobalance data storage requirements with imaging accuracy; (ii)discretizing into a grid of cells the surface above the targetformation, the dimensions of such surface cells being chosen relative toseismic shot point and receiver spacings so as to balance data storagerequirements with imaging accuracy; (iii) computing ray map files fromknown or assumed velocity distribution information, said filesrepresenting all physically significant ray paths connecting arepresentative point in a surface cell to a representative point in animage cell, using a velocity distribution for the subsurface region todetermine the ray paths, said ray map files containing at least thesurface cell to image cell travel time, the takeoff direction at eachsurface cell and the arrival direction at each image cell, saiddirections being specified in three-dimensional space; (iv) repeatingstep (iii) for each surface cell and each image cell; (v) storing theray map files in computer memory; (vi) interpolating travel times fromthe ray map files, said interpolated times being times from theparticular shot point and receiver locations associated with one seismicdata trace down to each point on the image point grid for each saidphysically significant ray path connecting same, said interpolationcomprising: interpolating a surface cell representative point near eachsaid particular shot point location and each said particular receiverpoint location; and interpolating an image cell representative pointnear said each point on the image grid; wherein said interpolations areimplemented using the ray direction information in the corresponding raymap file in order to ensure that interpolation is made between points onthe same branch of a travel time surface; (vii) repeating step (vi) foreach trace in the seismic data volume; and (viii) migrating the seismicdata using the interpolated travel times and the ray amplitudes.
 18. Themethod of claim 1, wherein the seismic data are migrated into datavolumes labeled by common azimuthal angle, or by common azimuthal angleand common reflection angle, and by one other label chosen from a listconsisting of common offset, common shot, and common receiver.
 19. Themethod of claim 1, further comprising selecting a velocity model for thesubsurface region, said velocity model providing P-wave or S-wave orboth velocities as a function of subsurface location, said model beingwith or without anisotropy parameters, wherein the velocity model isused for ray tracing in the ray-based imaging method in step (a). 20.The method of claim 1, wherein the mathematical relationships determinedin (b) yield an azimuthal angle that is measured relative to the raypair's dip direction at the image point, thereby resulting after imagingin (c) in azimuthal angles at points on the reflector surfaces that aremeasured relative to the dip direction of the reflector surface at anysuch point.
 21. A method for producing hydrocarbons from a subsurfaceregion, comprising: (a) obtaining data from a 3D seismic survey of thesubsurface region; (b) obtaining a processed version of the data whereinthe data were imaged using a method as described in claim 1, which isincorporated herein by reference, thus producing data volumes labeled byazimuth and reflection angle; (c) obtaining an interpretation of theimaged data wherein the interpretation used the azimuth data tointerpret structure in the subsurface region; and (d) drilling a wellinto the subsurface region and producing hydrocarbons based at leastpartly on the interpreted structure of the subsurface region.